1. Air Pressure and Winds III

2. Coriolis Force (Effect)
It is an apparent force;
Due to the rotation of the coordinate system (Earth);
It makes a moving object deflect from a straight line even in the absence of any forces acting on it.

3. Coriolis Force Demonstration
Rotating table A B
Dashed line - the trajectory of the chalk with respect to a non-rotating table.
Solid line - the trajectory of the chalk with respect to a rotating table.

4. The Magnitude of the Coriolis Force
The rotation of the Earth
The faster the planet rotates the bigger the force
The speed of the object
Bigger V -> bigger effect
The latitude:
Min. at the equator
Max. at the poles

5. Coriolis force as a function of:
The speed of the object
The latitude:
Min. at the equator
Max. at the poles

6. The Direction of the Coriolis Force
In the Northern hemisphere the deflection is to the right of the direction of motion.
In the Southern hemisphere the deflection is to the left of the direction of motion.
The winds in the Northern hemisphere will be deflected to the right and in the Southern hemisphere they will be deflected to the left.
Hurricanes spin differently in the Northern and Southern hemisphere

7. The Coriolis Force and the Earth
The Coriolis effect is important when moving over LARGE distances (air plane travel), with large velocities, away from the equator.

8. Centripetal/Centrifugal Force
Any motion in a curved path represents accelerated motion, and requires a force directed toward the center of curvature of the path. This force is called the centripetal force which means "center seeking" force.

9. Properties of the Centripetal Force
The centripetal acceleration, and the centripetal force are perpendicular to the direction of motion.
They only change the
direction of motion.
They do NOT change
the magnitude of the
velocity.
The Centripetal Force
changes the direction
of the wind but not the
magnitude of the wind.

10. Recap: Forces in the Atmosphere
Gravity force.
Vertical force in a downward direction
Atmospheric drag force (friction).
Acts against the motion
Proportional to velocity squared
Pressure gradient force
From high to low pressure regions
Perpendicular to the isobars
The bigger the pressure gradient (denser the isobars), the larger the pressure force
Coriolis force: due to the Earth’s rotation
Deflection to the right in the Northern hemisphere
Varies with latitude (absent at equator, max at the poles)
Proportional to the velocity of the object (wind)
Centripetal force:

11. Origin of the Centripetal Force
The centripetal force in the atmosphere is the net result of the pressure gradient force and the Coriolis force

12. Wind and Pressure Map

13. Winds in the Atmosphere
Geostrophic winds
Pressure gradient force = Coriolis force
Gradient winds
Pressure gradient force not equal to Coriolis force
Cyclones: PGF > CF
Anticyclones: PGF < CF
Surface winds
Affected by ground friction
Vertical air motion

14. Geostrophic Winds: direction
The pressure gradient force balances the Coriolis force.
Typically occur at higher altitudes (>1 km).
The winds are parallel to the isobars.
In the NH the low pressure is to the left of the wind direction and in the SH the low pressure is to the right.
Northern Hemisphere

15. Geostrophic Winds: speed
The wind speed is proportional to the density of the isobars – analogy to a water in a stream
Density of isobars increases -> PGF increases
Wind speed increases -> CF increases as well

16. Gradient Winds (Northern Hemisphere)
The net force acts as a centripetal force.
Anticyclonic flow
Cyclonic flow
Net force
Net force

17. Cyclonic Flow (flow around a low pressure center)
Clockwise in SH Counterclockwise in NH
Southern Hemisphere L
Northern Hemisphere

18. Winds Aloft in the Southern Hemisphere
Warm air above the equator and cold air above the polar regions
Higher pressure at the equator, lower pressure both to the north and to the south of the equator
The pressure gradient force is towards the poles, sets the air
in motion
The Coriolis force
NH: to the right
SH: to the left
The wind turns right in the NH and left in the SH, becomes parallel to the isobars
Westerly winds in both the Northern and Southern Hemispheres.

19. Summary: prevailing winds at high altitudes
Direction
Zonal: E-W
Meridional: N-S
Balance of forces
Geostrophic: near straight isobars
Gradient: near curved isobars

20. Surface Winds-a balance of three forces
In the boundary layer (~1km thick) friction is important!
Friction is acting opposite the direction of the velocity -> friction reduces the wind speed -> the Coriolis force becomes weaker -> it cannot balance the pressure force.
The wind starts to blow across the isobars towards the low pressure
The angle between the direction of the wind and the isobars is on average 30 deg. It depends on the topography.

21. Is this a surface or a high-altitude map? Which hemisphere is this?
Surface map in the Northern hemisphere

22. Buys-Ballot’s Law
Turn your back to the wind, then turn clockwise 30 deg. The center of low pressure is on your left.
W. Ferrel
Buys Ballot
James Coffin

23. Vertical Air Motion: Convergences and Divergences
Near a center of low surface pressure there is a convergence of air -> the air is forced to rise and then diverge at higher altitudes. The opposite takes place near a center of high surface pressure.

24. Hydrostatic Equilibrium
On average gravity is balanced by the pressure gradient force -> hydrostatic equilibrium
Small deviations from hydrostatic equilibrium result in small vertical winds (a few cm/s)